WATER QUALITY ASSESSMENT IN THE GALLINAS WATERSHED, …

WATER QUALITY ASSESSMENT IN THE GALLINAS

WATERSHED, LAS VEGAS, NEW MEXICO

RESEARCH AND REPORT WRITTEN BY: Thomas Evans, Environmental Science and Management Major Dr. Jennifer Lindline, Associate Professor of Geology and Faculty Advisor Natural Sciences Department Environmental Geology Program New Mexico Highlands University P.O. Box 9000 Las Vegas, NM 87701 505.426.2046

SUBMITTED:

October 15, 2004

2

TABLES AND FIGURES

Table 1 Parameters measured for water analyses and analytical methods used………...15

Table 2 Hardness and alkalinity data……………………………………………………16

Table 3 Water chemistry and analytical results…………...…………………………17-18

Table 4 Mixing calculations ……………………………….……………………………19

Figure 1 Map of the study are and sample locations……………………………………20

Figure 2 Photographs of the region and sample locations…………………………...21-22

Figure 3 Stratigraphic column and cross-section of Gallinas watershed geology……...23

Figure 4 Radial plots comparing Ca-Cl-SO4-Na concentrations in sampled waters…....24

Figure 5 Histogram showing major cations in the sampled waters……………………..25

Figure 6 Histogram showing major anions in the sampled waters…………….………..26

Figure 7 Histogram showing dissolved mineral concentrations in the sampled waters...27

Figure 8 Histogram showing hardness, conductivity, and total dissolved solid (TDS)

measurements in the sampled waters………………………………………......28

Figure 9 Graph comparing total dissolved solids and conductivity in the sampled

waters………………………………………………………………………….29

3

ABSTRACT

This research was conducted to evaluate water quality conditions within the Gallinas

Watershed. The Gallinas River originates in Precambrian crystalline rocks of the

southern Sangre de Cristo Mountains and flows southeast toward Paleozoic and

Mesozoic strata of the Las Vegas basin. The Gallinas River is the primary source of

water for Las Vegas, NM, providing 95% of its domestic water supply. Additional

surface water is diverted to the Storrie Lake Water Project and divided among multiple

users, including the Las Vegas National Wildlife Refuge, farmers, and ranchers.

Seven surface water samples were collected from the Gallinas River beginning in the

upper headwaters and ending downstream of the Las Vegas wastewater treatment plant.

Additional surface water samples were collected from Storrie and McCallister Lakes, two

Storrie Lake Water Project diversions. Representative indicator parameters Ca, Na, Cl,

and SO4 increase from 11.8-142, 4.5-92.3, 1.3-62.2, and 9.9-450 mg/L respectively from

the headwaters to the lower river sites. Likewise, hardness, alkalinity, conductivity, and

total dissolved solids are appreciably higher in the lower Gallinas River. These results

demonstrate a correlation between water quality degradation and percentage of exposed

sedimentary rocks with which the Gallinas River comes into contact.

An interesting observation is the dramatic degradation in water quality at McCallister

Lake, the largest surface water body at the Las Vegas National Wildlife Refuge. Data

show elevated concentrations of Ca (402), Na (1165), Cl (678), SO4 (3525) (mg/L) and

conductivity (11,200 micromohs/cm). Thenardite precipitates along the shoreline during

the summer and fall indicating that localized zones of saturation for Na and SO4 exist

seasonally within the shallow lake. Ground water samples collected from seeps along the

Gallinas River canyon and down gradient of McCallister Lake show all indicator

parameters occur at concentrations intermediate between those of McCallister Lake and

local domestic wells. These data suggest that water within the seeps is the blending of

surface water that infiltrates from the lake and mixes with ground water before

discharging to the lower Gallinas River. Further study of evaporation effects as well as

4

anthropogenic and natural aquifer contributions to water quality is warranted to improve

water management practices within the Gallinas Watershed.

INTRODUCTION Gallinas River is a tributary of the Pecos River Stream System in northern New Mexico

that yields an average of 3,100 acre-feet of water annually (Montoya 2000). The Gallinas

River originates in the southern Sangre de Cristo Mountains and flows southeast towards

the high plains desert community of Las Vegas. A large percentage of flow is diverted to

the Storrie Lake Water Project and divided among multiple users, including the city of

Las Vegas, Las Vegas National Wildlife Refuge, farmers and ranchers. Continuing and

growing demands for water necessitate that the Gallinas River be managed for water

production and protection of water quality.

Garn and Jacobi (1996) presented baseline water quality data for the Gallinas River and

related water quality characteristics to spatial differences in the geology of the watershed.

We aimed to expand upon their study and examine the spatial changes in water quality

throughout a greater portion of the watershed. We wanted to look particularly at the

impacts of water quality within the Storrie Lake Water Project diverted water system.

We collected seven surface water samples from the Gallinas River starting at the upper

headwaters and ending downstream of the Las Vegas wastewater treatment plant (Figs. 1,

2). Additional surface water samples were collected from Storrie and McCallister Lakes,

two Storrie Lake Water Project diversions. Ground water samples were collected from

natural springs along lower Gallinas canyon and a local domestic well. All water

samples were analyzed for dissolved minerals, salts, metals, cations and anions. The

results were plotted on histograms and radial plots to assess water quality changes

throughout the watershed.

PROJECT GOALS The general objective of this study was to examine the spatial changes in water quality

throughout the Gallinas Watershed. The specific project goals include:

• Collect baseline surface water and ground water data within the Gallinas watershed.

5

• Evaluate changes in water quality from the upper mountain headwaters to

downstream urban center (Las Vegas) and diversion points (Storrie Lake Water

Project).

• Assess natural contributions to spatial variability in water quality.

• Evaluate changes in water quality along a ground water flow path that originates

within surface locations at the Las Vegas National Wildlife Refuge (McCallister

Lake) and extends through a shallow bedrock aquifer before discharging as seeps

along lower Gallinas Canyon.

STUDY AREA Gallinas Watershed

The Gallinas Watershed is located between the Canadian River Watershed to the east and

the Rio Grande Watershed to the west and covers an area of 52,500 acres. The Gallinas

River originates at an elevation of 11,661 feet at Elk Mountain on the eastern flanks of

the Sangre de Cristo Mountains. The stream flows to the southeast through the city of

Las Vegas before merging with the Pecos River.

Land ownership within the Gallinas watershed is subdivided among private (21%),

federal (62%), and state/county entities (17%) (Montoya, 2000). The land is primarily

designated as federal forest land (62%) and supports recreation, wetlands, wildlife habitat

and timber harvesting. The remaining watershed land area supports municipal, domestic,

and irrigation supplies. Gallinas River is the primary water supply for the City of Las

Vegas, New Mexico (population 16,000).

Geology

The study area is situated on the Great Plains where the prairie meets the Rocky

Mountains. The region consists of native grasslands, farm and ranch lands, marshes,

ponds, timbered canyons and streams. The region is primarily underlain by Cretaceous

age (~65-145 million year old) rock formations and Tertiary age (~65 million year old to

present) alluvium and gravel deposits (Fig. 3). The Cretaceous Dakota Group, Graneros

Shale, Greenhorn Limestone, Carlile Shale and Niabrora Shale uncomformably overlie

6

Paleozoic sedimentary strata and Precambrian crystalline rocks. The Paleozoic and

Cretaceous strata strike due north through the Las Vegas area and are steeply dipping and

overturned to the west (Baltz, 1972) (Fig. 3). The units fold at depth into an

asymmetrical syncline that defines the Las Vegas sub basin of the Raton sedimentary

basin. East of Las Vegas, the stratigraphic units lie horizontally. The following rock

descriptions, from oldest to youngest, are summarized from Lessard and Bejnar (1976).

Dakota Group The Dakota Group is divided into the Lower Sandstone Unit, Middle

Shale Unit, and the Upper Sandstone Unit. The Lower Sandstone Unit is a cross-

stratified quartz arenite. It is coarse- to fine-grained and ranges in color from a grayish-

orange to a light gray. The Middle Shale Unit comprises silty, quartz arenite combined

with black carbonaceous shale. The Upper Sandstone Unit is a fine- to medium-grained,

pale colored well-cemented highly resistant quartz arenite. It is tilted on end in the

central portion of the study area and defines the north-striking Creston Ridge. The

Dakota Group is approximately 36.9 m thick and outcrops along the highest levels of

Gallinas Canyon.

Graneros Shale and Greenhorn Limestone The Graneros Shale is 68.6 m thick. It is

comprised of alternating fine sandstone, siltstones, and shales. The Graneros Shale is

easily weathered and typically outcrops as a valley fill. The unit forms a gradational

contact with the Greenhorn Limestone, a light gray colored unit that consists of

interbedded limestone and calcareous shale. The Greenhorn Limestone underlies the

drainages within the lower Gallinas canyon and is the predominant source of ground

water seepage in the study area.

Carlile Shale The Carlile Shale is an approximately 67.0 m thick dark gray shale unit

that consists of yellow-brown cross-laminated arenite that contains shallow water fossils.

Niobrara Formation The Niobrara Formation is 185.0 m thick and includes dark colored

shales and fine-grained siltstones interbedded with thin layers of limestone. This unit

7

outcrops around Storrie Lake and contains abundant freshwater fossils including shark

teeth, ray teeth, ammanoid shell impressions and various shelly fauna.

RESEARCH METHODS Surface water and ground water samples were collected in prewashed Nalgene bottles.

The bottles were filled to the rim with water, capped, and placed on ice. The water

samples were delivered to Albuchemist Laboratories, Albuquerque, New Mexico, for

multiple mineral analyses as well as pH, conductivity, and total dissolved solids

measurements. Duplicate samples were collected at each site for hardness and alkalinity

tests at New Mexico Highlands University laboratories. Table 1 is a list of the

parameters that were measured, with reference to the analytical methods used.

Hardness and Alkalinity

Hardness and alkalinity tests were conducted at New Mexico Highlands University

laboratories by Evans. The formulas and the procedures for measuring each were taken

from Standard Methods for the Examination of Water and Wastewater, 20th edition

(1998). Hardness tests determine the amount of calcium and magnesium salts in water.

Standard titration methods were employed using 25 milliliters (mL) of sample. Hardness

values were calculated using the following formula:

Hardness (mg CaCO3/L) = A x B x 1,000/mL sample

where A = mL titration for sample and

B = mg CaCO3 equivalent to 1.00 mL EDTA titrant.

Note:

B = 1.50 mg CaCO3 for 0.015 M EDTA (Trial 1) and

B = 0.98 mg CaCO3 for 0.015 M EDTA (Trial 2).

Alkalinity is the total concentration of bases in water and the ability of water to neutralize

acids. Standard titration methods were employed utilizing 100 mL of sample. Alkalinity

values were calculated using the following formula:

8

Alkalinity (mg CaCO3/L) = A x N x 50,000/mL sample

where A = mL standard acid used and

N = normality of standard acid (0.02 M).

RESULTS All water chemistry results are listed in Tables 2 and 3 and shown on Figs. 4-8. A

summary of the results follows.

Calcium, Magnesium, and Sodium

Major cation concentrations show a general increase in a downstream direction

throughout the watershed. Calcium (Ca), magnesium (Mg), and sodium (Na) increase

from 11.8-142, 2.0-33.3 and 45.0-92.3 mg/L respectively from the headwaters to the

lower river sites. Gallinas Canyon ground water seeps show high values of Ca (209

mg/L), moderate values of Mg (51.2 mg/L) and moderate values of Na (148 mg/L).

Storrie Lake had moderate cation concentrations (Ca 92.4 mg/L, Mg 19.9 mg/L, and Na

44.0 mg/L). The Montezuma Hot Springs had high Na concentration (190 mg/L).

Storrie Lake had the highest major cation concentrations (Ca 402.0 mg/L, Mg 365.5

mg/L, and Na 1188 mg/L).

Iron

All surface water and ground water samples contained less than 1.0 mg/L of iron (Fe) and

were within the drinking water safety limits of 0.3 mg/L concentration (Brooks, Folliott,

Gregersen, & DeBano, 1997). Ground water Fe values were typically below the

laboratory detection limits (<0.05 mg/L). Storrie Lake had higher Fe values than

McCallister Lake (0.63 and 0.09 mg/L respectively).

Chloride

Chloride (Cl) concentrations show a general increase in a downstream direction

throughout the watershed. Cl increased from 1.3 to 68.8 mg/L from the Upper Gallinas

River to the Lower Gallinas River sampling sites. The Gallinas Canyon ground water

9

seeps showed an average Cl concentration of 111 mg/L. Storrie Lake showed relatively

low Cl concentrations (13.9 mg/L) while McCallister Lake had the highest Cl

concentrations (693 mg/L).

Sulfate

Sulfate (SO4) values increased from the Upper Gallinas River (9.9 mg/L) downstream to

San Augustine (450 mg/L). Ground water discharging from Gallinas Canyon seeps

showed high SO4 concentrations (average 628 mg/L). Storrie Lake had moderate SO4

concentrations (206 mg/L) while McCallister Lake had extremely high SO4

concentrations (3585 mg/L).

Bicarbonate

Bicarbonate (HCO3) values increased throughout the watershed from the Upper Gallinas

River (44.5 mg/L) downstream to St. Augustine (214 mg/L). Ground water draws along

the canyon showed high HCO3 values, averaging 266 mg/L. Storrie Lake and

McCallister Lake had moderate HCO3 values (150.25 and 113 mg/L respectively).

Nitrate

Most nitrate nitrogen (as N) values throughout the study area were very low (< 1.0 N

mg/L). Nitrate showed a general increase in a downstream direction throughout the

watershed from 0.11 N at the Upper Gallinas River site to 6.91 at the Lower Gallinas

River site. Note that these values are below the New Mexico Water Quality Standards of

< 10.0 mg/L (New Mexico Water Quality Control Commission, 1991).

Hardness

Water hardness is described qualitatively using the following scale: soft water, 0-60

mg/L; moderately hard, 61-120 mg/L; hard, 121-180 mg/L; very hard, more than 180

mg/L (Brooks and others, 1997). Surface water samples increased in hardness from the

Upper Gallinas to Lower Gallinas River sites. Surface water from the Hermit’s Peak

Trailhead (37.7 mg CaCO3/L) and Hot Springs (6.4 mg CaCO3/L) were soft, while water

from the Skating Pond to the St. Augustine increased from 85.7 to 487 mg CaCO3/L.

10

Ground water samples from the Gallinas Canyon seeps were very hard, averaging 733 mg

CaCO3/L. Storrie Lake and McCallister Lake were also very hard, with hardness values

of 282 and 2495 CaCO3/L respectively.

Alkalinity

Waters in the study area had alkalinity values ranging from 36.7 to 227 CaCO3.

Alkalinity increased throughout the watershed from the Upper Gallinas (36.7 CaCO3) to

Lower Gallinas River (185 CaCO3) sites. Alkalinity was highest in the ground water

discharging from the canyon seeps, averaging 221 CaCO3. Storrie Lake (127 CaCO3)

and McCallister Lake (121 CaCO3) had moderate alkalinity values.

pH

All of the water samples were slightly alkaline, having pH values between 7.35 and 8.37.

Conductivity and Total Dissolved Solids

Conductivity is a measurement of the ability of an aqueous solution to carry an electrical

current. The higher the concentration of total dissolved solids (TDS) in a water sample,

the higher its conductivity. Conductivity and TDS are strongly correlated throughout the

study area (R2 = 0.9975) (Fig. 9). Conductivity and TDS increase in a downstream

direction throughout the watershed (110 to 1610 micromohs/cm and 76 to 1018 mg/L

respectively). Storrie Lake shows moderate to high conductivity (975 micromohs/cm)

and TDS (513 mg/L) while McCallister Lake shows extremely high conductivity (11000

micromohs/cm) and TDS (7313 mg/L).

DISCUSSION

The composition of stream water often reflects the composition of the drainage-basin

geology with which the water has been in contact. Major cations (Ca, Mg, Na), anions

(Cl and SO4), and other indicator parameters increase in the Gallinas River in a

downstream direction illustrating the differences in geology in the watershed. Water

quality shows little change over an approximately 20 kilometer stretch from the Upper

Gallinas Source to the Montezuma Skating Pond. Throughout this reach, the river flows

11

over Precambrian crystalline rocks (granites, granitic gneisses, amphibolites and schists)

which contain silicate minerals having low solubilities and slow responses to weathering.

Water quality degrades markedly in terms of dissolved NaCl and CaSO4 and other water

parameters from the Montezuma Pond to the Lower Gallinas River sampling sites over an

approximately 40 kilometer stretch. Along this expanse, the river flows over Cretaceous

limestones and limey shales of the Niabrora, Carlile, Greenhorn and Graneros formations.

The sedimentary rocks are more permeable than the crystalline rocks of the upper

watershed and contain major amounts of highly soluble calcite (CaCO3) and minor

amounts of gypsum (CaSO4). Some of the elevated NaCl concentrations are attributed to

the Montezuma Hotsprings, which issue Na- and Cl- rich waters to the river.

Storrie Lake and McAllister Lake exhibit extremely high concentrations of dissolved Na,

Cl, Ca, and SO4 compared to other surface water and ground water samples throughout

the watershed. We ascribe these high salt concentrations to evaporation effects. As the

lake levels lower during low precipitation periods (summer and winter), the bedrock is

exposed. Calcium, magnesium, and sodium salts are leached from the limestones and

lime-rich shales underlying the region. With continuous evaporation, soils become dry

and salt efflorescence occurs (NDSP, 2004), explaining the presence of thenardite on

Melton Pond (Evans and Lindline, 2003). Subsequent precipitation events can cause

runoff that is rich in dissolved salts to enter the lake. While Storrie Lake shows high

concentrations of dissolved minerals, the concentrations were much lower than at

McCallister Lake. There is apparently a larger flux of water through Storrie Lake from

small stream drainages and landscape runoff than to McCallister Lake. This large flux of

fresh water dilutes the dissolved mineral concentration at Storrie Lake. McCallister

Lake, however, relies solely on allotments of water from the Storrie Lake Water Project.

The water contributions to the system are not sufficient to balance evaporation effects.

The high salt concentrations in McCallister Lake have serious implications regarding the

health and stability of the Las Vegas National Wildlife Refuge. The refuge hosts over ten

lakes ranging from 0.10 to 1.10 kilometers in diameter that provide habitat for a wide

variety of plants, migratory birds and other wildlife. Increasing salt concentrations in the

12

lakes and soils limit nutrient uptake by biota. Saline conditions place environmental

stress on riparian flaura and fauna and threaten the vitality of the refuge lake ecosystem.

Cations, anions and other water parameters are relatively higher in Gallinas Canyon

ground water seeps than most surface water samples. We attribute the high chemical

load in the seeps to dissolved loading in the subsurface. Infiltrated water enters the

subsurface as storage through primary matrix porosity, but is transmitted through vertical

fractures, joints, and bedding plane separations. Groundwater has a longer residence time

in contact with bedrock and thus the potential to dissolve minerals during transit. That

water subsequently gets released from storage, migrates through fractures, and discharges

along seepage faces of Gallinas Canyon.

We explored the possibility that water that drains from McCallister Lake into the

subsurface contributes to chemical loading of ground water. We collected a ground water

sample from a local domestic well (Charles R. Ranch) and compared its chemistry to the

chemistry of McCallister Lake and the Gallinas Canyon seeps (Table 4). The local

ground water shows lower Na, Ca, Cl, and SO4 concentrations than the ground water

seeps. We applied a least squares mixing model to calculate the composition of a

solution resulting from mixing various proportions of McCallister Lake water and

Charles R. Ranch ground water. Our results indicate that the ground water seeps have an

average composition approaching a blend of 14% McCallister Lake water and 86%

ground water (Table 4). These results suggest that infiltration from McCallister Lake is

relatively minor contributor to chemical loading to the lower Gallinas River.

CONCLUSION As hypothesized, the water chemistry throughout the Gallinas Watershed is degrading

from the river’s headwaters to lower river sites probably due to difference in the geology

in the watershed. From the Upper Gallinas River site to the Montezuma Pond, the river

drains predominantly from low permeable, weathering resistant crystalline rocks. For the

remainder of the watershed studied, the river drains highly permeable calcite- and

gypsum-bearing sedimentary rock formations which contribute Ca, SO4, HCO3 and other

13

chemical species to surface and ground water supplies. Well log data are necessary to

understand the contribution of individual hydrostratigraphic units to chemical loading

within the watershed.

Ground water seeps discharging along the Gallinas River canyon have chemical

signatures approaching a mixture of 14% surface water (McCallister Lake) and 86%

ground water (local domestic well). Mixing calculations indicate that vertical leakage

from McCallister Lake is a relatively minor contributor to ground water recharge and

subsequently, chemical loading to the Lower Gallinas River.

Of note are the elevated Ca, Na, Cl, SO4 concentrations and conductivity and TDS

measurements at McCallister Lake. These data suggest that high evaporation rates

relative to water input rates are enriching dissolved salt concentrations at McCallister

Lake and other surface water reservoirs at the Las Vegas National Wildlife Refuge.

Continued drought conditions will enhance evaporation rates at the refuge and lead to

increasing accumulation of dissolved salts and minerals, potentially threatening the

vitality of the refuge ecosystem. As saline soils place an environmental stress on riparian

flaura and fauna, surface water conveyance operations at the Las Vegas National Wildlife

Refuge need to be optimized to reduce evaporation effects at McCallister Lake. A

comprehensive water and chemical budget analysis is needed to examine the factors

influencing water quality and improve management practices at the refuge. With a

limited water supply, the city of Las Vegas, Storrie Lake Water Project, and other

Gallinas River users face issues concerning the conservation of its most potable resource.

ACKNOWLEDGMENTS We gratefully acknowledge the New Mexico Water Resources Research Institute for

financial support of this project. We also acknowledge the NASA Future Researchers

Initiative and the Department of Energy for additional financial assistance. We thank

Werner Muller for guiding us on our first sampling excursion and allowing us access to

his property for water sampling. We also thank Daryl Williams for his involvement in

the second phase of the field and laboratory research.

14

REFERENCES Baltz, E. H., 1972, Geologic map and cross sections of the Gallinas Creek area, Sangre de

Cristo Mountains, San Miguel County, New Mexico: U.S. Geological Survey

Miscellaneous Geological Investigations, Map 1-673.

Brooks, K.N., Folliot, P.F., Gregersen, H.M., & DeBano, L.F., 1997. Hydrology and the

management of watersheds. Second edition. Ames: Iowa State University Press.

Evans, T. and Lindline, J., 2003. Influence of infiltration and evaporation on the

hydrologic budget at the Las Vegas National Wildlife Refuge, New Mexico. Poster

presentation at the New Mexico Geological Society 2003 Spring Conference.

Garn, H.S. and Jacobi, G.Z., 1996, Water quality and benthic macroinvertebrate

bioassessment of Gallinas Creek, San Miguel County, New Mexico, 1987-1990, U.S.

Geological Survey Water-Resources Investigations Report 96-4011, 57 p.

Lessard, R.H. and Bejnar, W., 1976. Geology of the Las Vegas area, in Vermejo Park:

NMGS 27th Field Conference Guidebook, p. 103-108.

Montoya, L., 2000. Water, growth, and sustainability: planning for the 21st century.

New Mexico Water Resources Research Institute Report No. 319.

New Mexico Water Quality Control Commission, 1991, Water quality standards for

interstate and intrastate streams in New Mexico: Santa Fe, WQCC 91-1, 49 p.

National Dryland Salinity Program (2004, January 1). Salt-affected soils. Retrieved

January 11, 2004 from http://www.ndsp.gov.au.

Standard Methods for the Examination of Water and Wastewater, 20th edition (1998).

Table 1. Parameters measured for water analyses and analytical methods used. The analytical methods listed refer to page numbers in the Standard Methods for the Examination of Water & Wastewater, 18th edition (1992).

PARAMETER ANALYTICAL METHODS* Calcium 3111.B Magnesium 3111.B Sodium 3500-NaD Iron 3111.B Hardness (as CaCO3) 2340.B Sulfate 4500-SO4E Chloride 4500-Cl D Carbonate 2320.B Bicarbonate 2320.B Alkalinity (as CaCO3) 2320.B pH 4500-H B Conductivity (micromhos/cm) 2510.B Total dissolved solids 2540.B Nitrate (as N) 4500-NO3. E Fluroide 4500-F. D Silica 4500-Si D

16

Table 2. Hardness and Alkalinity data comparing results from Albuchemist and New Mexico Highlands University laboratories.

HARDNESS

Site Albuchemist NMHU (Avg) AVERAGE ST DEV PRECISION %

Lower Gallinas 453 494 473.5 29.0 6.1 Gallinas Canyon Seep 1 763 800 781.5 26.2 3.3 Gallinas Canyon Seep 2 704 708 706.0 2.8 0.4 Gallinas Canyon Seep 3 723 755 739.0 22.6 3.1 Gallinas Canyon Seep 4 740 722 731.0 12.7 1.7 McCallister Lake 2535 2286 2410.5 176.1 7.3 Storrie Lake 330 330 329.9 0.1 0.0

ALKALINITY

Site Albuchemist NMHU (Avg) AVERAGE ST DEV PRECISION %

Lower Gallinas 160 166 163.0 4.2 2.6 Gallinas Canyon Seep 1 214 200 206.8 10.3 5.0 Gallinas Canyon Seep 2 222 212 216.8 7.4 3.4 Gallinas Canyon Seep 3 222 219 220.5 2.1 1.0 Gallinas Canyon Seep 4 227 226 226.5 0.7 0.3 McCallister Lake 99 90 94.3 6.1 6.4 Storrie Lake 140 134 136.8 3.9 2.8

17

Table 3. Water chemistry analytical results. Site descriptions correspond to tags on site map (Figs. 1 and 4). SAMPLE / SITE DESCRIPTION Ca Mg Na Si Fe Cl mg/L mg/L mg/L mg/L mg/L mg/L TE03-27/S16 Hermits Peak Trailhead 11.8 2 4.5 11.4 0.19 1.3 TE03-28/S17 Skating Pond 30.4 2.4 6.3 4.0 <0.05 2.5 TE03-30/S18 Hot Springs 3.9 <0.5 190 18.4 <0.05 151 TE0-33/S19 Middle Gallinas River 1 56.4 7.12 37.5 10.8 0.13 32.5 TE0-34, 35/S20 (avg) Middle Gallinas River 2 105 27.1 54.7 5.5 <0.05 0.83 TE03-1/S1 Lower Gallinas River 131 30.7 92.3 3.2 0.17 62.2 TE0-36, 37/S21 (avg) St Augustin 142.5 33.3 78 1.8 <0.05 68.8 TE03-3/S2 Gallinas Canyon Seep 1 212 56.8 142 12.1 <0.05 125 TE03-12/S9 Gallinas Canyon Seep 2 207 45.4 154 13.4 <0.05 102 TE03-14/S10 Gallinas Canyon Seep 3 205 51.4 140 23.3 0.09 108 TE03-16/S11 Gallinas Canyon Seep 4 212 51.1 155 9.2 <0.05 109 TE03-18, 22/S12 (avg) McCallister Lake (Nov03) 402 371.5 1165 3.6 0.09 678 TE03-38, 39/S12 (avg) McCallister Lake (March04) 384.5 357.5 1210 0.3 ----- 709 McCallister Lake (avg) 393.3 364.5 1188 1.9 0.09 693 TE03-20, 23/S13 (avg) Storrie Lake (Nov 03) 92.4 24.2 42.5 11.1 0.63 13.1 TE03-40, 41/S13 (avg) Storrie Lake (March04) 67.6 15.6 45.5 0.4 ----- 14.6 Storrie Lake (avg) 80.0 19.9 44.0 5.7 0.63 13.9 SAMPLE / SITE DESCRIPTION F SO4 CaCO3 Bicarbonate Nitrate Hardness mg/L mg/L mg/L mg/L as N as CaCO3 TE03-27/S16 Hermits Peak Trailhead 0.52 9.9 <1.0 44.5 0.11 37.7 TE03-28/S17 Skating Pond 0.43 13.3 2.1 121 0.11 85.7 TE03-30/S18 Hot Springs 26.7 38.5 1.4 117 0.04 6.4 TE0-33/S19 Middle Gallinas River 1 2.69 66.4 3.3 159 0.04 170 TE0-34, 35/S20 (avg) Middle Gallinas River 2 64.8 286 1.0 171 0.05 309 TE03-1/S1 Lower Gallinas River 0.86 348 <1 195 6.91 453 TE0-36, 37/S21 (avg) St Augustin 0.78 450 6.0 214 2.18 487 TE03-3/S2 Gallinas Canyon Seep 1 0.95 660 3.3 258 0.22 763 TE03-12/S9 Gallinas Canyon Seep 2 0.95 603 2.5 267 0.96 704 TE03-14/S10 Gallinas Canyon Seep 3 0.92 630 2.3 267 0.71 723 TE03-16/S11 Gallinas Canyon Seep 4 0.94 619 3.5 272 0.50 740 TE03-18, 22/S12 (avg) McCallister Lake (Nov03) 3.38 3525 60.0 59 0.04 2535 TE03-38, 39/S12 (avg) McCallister Lake (March04) 2.99 3645 4.3 167 0.06 2455 McCallister Lake (avg) 3.18 3585 32.2 113 0.05 2495 TE03-20, 23/S13 (avg) Storrie Lake (Nov 03) 1.14 190 2.4 168 0.06 330 TE03-40, 41/S13 (avg) Storrie Lake (March04) 1.06 223 4.0 133 0.08 233 Storrie Lake (avg) 1.10 206 3.2 150 0.07 282

18

Table 3. Water chemistry analytical results continued.

SAMPLE / SITE DESCRIPTION Alkalinity pH Conductivity TDS T ANIONS T CATIONS as CaCO3 mg/L micromhos/cm mg/L TE03-27/S16 Hermits Peak Trailhead 36.7 7.4 110 76 1.00 0.97 TE03-28/S17 Skating Pond 103 8.5 230 108 2.35 1.97 TE03-30/S18 Hot Springs 100 8.2 1050 492 8.41 8.46 TE0-33/S19 Middle Gallinas River 1 135 8.4 595 332 5.05 5.04 TE0-34, 35/S20 (avg) Middle Gallinas River 2 141 7.9 1265 784 12.19 9.85 TE03-1/S1 Lower Gallinas River 160 7.4 1380 780 12.35 13.08 TE0-36, 37/S21 (avg) St Augustin 185 8.4 1610 1018 16.56 13.24 TE03-3/S2 Gallinas Canyon Seep 1 214 8.1 2800 1440 21.55 21.43 TE03-12/S9 Gallinas Canyon Seep 2 222 8.0 2200 1256 19.87 20.76 TE03-14/S10 Gallinas Canyon Seep 3 222 8.0 2400 1348 20.60 20.55 TE03-16/S11 Gallinas Canyon Seep 4 227 8.0 2600 1352 20.48 21.53 TE03-18, 22/S12 (avg) McCallister Lake (Nov03) 99 8.1 11200 7060 93.65 101.30 TE03-38, 39/S12 (avg) McCallister Lake (March04) 143 8.2 10800 7566 98.79 101.23 McCallister Lake (avg) 121 8.1 11000 7313 96.22 101.27 TE03-20, 23/S13 (avg) Storrie Lake (Nov 03) 140 8.1 1030 504 7.13 8.47 TE03-40, 41/S13 (avg) Storrie Lake (March04) 115 8.2 920 522 7.28 6.63

Storrie Lake (avg) 127 8.1 975 513 7.21 7.55 SAMPLE / SITE DESCRIPTION NaCl CaSO4 SiO2 CaCO3 CaMg(CO3)2 mg/L mg/L mg/L mg/L mg/L TE03-27/S16 Hermits Peak Trailhead 2.1 14.0 8.45 11.42 15.15 TE03-28/S17 Skating Pond 4.1 18.4 3.07 51.50 18.18 TE03-30/S18 Hot Springs 249 55.3 13.83 ----- ----- TE0-33/S19 Middle Gallinas River 1 54.5 93.6 8.45 41.85 53.77 TE0-34, 35/S20 (avg) Middle Gallinas River 2 1.4 406 4.23 ----- ----- TE03-1/S1 Lower Gallinas River 103 493 2.46 ----- ----- TE0-36, 37/S21 (avg) St Augustin 1.3 638 1.38 ----- ----- TE03-3/S2 Gallinas Canyon Seep 1 206 936 9.30 ----- ----- TE03-12/S9 Gallinas Canyon Seep 2 168 855 10.30 ----- ----- TE03-14/S10 Gallinas Canyon Seep 3 178 893 17.90 ----- ----- TE03-16/S11 Gallinas Canyon Seep 4 180 878 7.07 ----- ----- TE03-18, 22/S12 (avg) McCallister Lake (Nov03) 1118 4998 2.73 ----- ----- TE03-38, 39/S12 (avg) McCallister Lake (March04) 1170 5168 0.27 ----- -----

McCallister Lake (avg) 1144 5083 1.50 ----- ----- TE03-20, 23/S13 (avg) Storrie Lake (Nov 03) 21.6 269 8.53 ----- ----- TE03-40, 41/S13 (avg) Storrie Lake (March04) 24.1 315 0.28 ----- -----

Storrie Lake (avg) 22.9 292 4.40 ----- -----

19

Table 4. Results from step-wise mixing of McCallister Lake (Solution 1) and Charles R. Ranch well water (Solution 2). Mixing of 14% lake sample water with 86% well water sample yields a mixture that closely matches average Gallinas Canyon seep water.

NA CA CL SO4 (mg / L) (mg / L) (mg / L) (mg / L) Solution 1 McCallister Lake 1165.0 402.0 678.0 3525.0 Solution 2 CRR Well 38.0 76.1 28.9 98.0 Optimized Sample Gallinas Canyon Seeps (avg) 147.8 209.0 111.0 628.0 Mixing Results 14% Sol 1; 86% Sol 2 195.8 121.7 119.7 577.8 Percent Difference (calculated versus measured) 24.5 71.7 7.3 8.7

20

Figure 1. Topographic map of the region showing water sampling localities.

HHoott SSpprriinnggss

SSaann AAuugguussttiinnee

LLoowweerr GGaalllliinnaassRReecceeppttoorr

GGrroouunndd WWaatteerr SSeeeeppss

UUppppeerr GGaalllliinnaass SSoouurrccee

MMiiddddllee GGaalllliinnaass 11

MMoonntteezzuummaa PPoonndd


MMccCCaalllliisstteerr LLaakkee GGaalllliinnaass DDiivveerrssiioonn 22

SSttoorrrriiee LLaakkee GGaalllliinnaass DDiivveerrssiioonn 11

CRESTON RIDG

CChhaarrlleess RR.. RRaanncchh

21

VViieeww ooff GGaalllliinnaass CCaannyyoonn llooookkiinngg ssoouutthhwwaarrdd..

MMiiddddllee GGaalllliinnaass RRiivveerr ((11)) aass iitt ppaarraalllleellss NNaattiioonnaall AAvveennuuee iinn tthhee ttoowwnn ooff LLaass VVeeggaass,, NNMM..

MMoonntteezzuummaa ppoonndd..

UUppppeerr GGaalllliinnaass RRiivveerr;; HHeerrmmiitt’’ss PPeeaakk ttrraaiillhheeaadd..

MMoonntteezzuummaa hhoott sspprriinnggss.. GGaalllliinnaass RRiivveerr fflloowwss tthhrroouugghh cceenntteerr ooff pphhoottooggrraapphh..

MMiiddddllee GGaalllliinnaass RRiivveerr ((22)) aass iitt fflloowwss uunnddeerr BBrriiddggee SSttrreeeett iinn tthhee ttoowwnn ooff LLaass VVeeggaass,, NNMM..

22

Figure 2. Photographs of the region and sampling locations.

GGaalllliinnaass DDiivveerrssiioonn 11;; SSttoorrrriiee LLaakkee..

GGrroouunndd wwaatteerr sseeeepp aalloonngg lloowweerr ccaannyyoonn rriimm..

GGaalllliinnaass DDiivveerrssiioonn 22;; MMccCCaalllliisstteerr LLaakkee.. NNoottee tthhee wwhhiittee ssaallttss oonn tthhee sshhoorree iinn tthhee lleefftt hhaanndd ppoorrttiioonn ooff tthhee pphhoottooggrraapphh..

LLoowweerr GGaalllliinnaass RRiivveerr aatt SSaann AAuugguussttiinnee..

23

Figure 3. Upper: Abbreviated stratigraphic column denoting the units that outcrop throughout the study area (Lessard and Bejnar, 1976). Lower: Cross-section showing the major rock types that make up the subsurface geology and their structural form (Baltz, 1972).

24

Figure 4. Radial plots comparing the relative concentrations of Ca-Cl-SO4-Na (mg/L) in sampled waters. Major cation and anion concentrations increase from the Upper Gallinas Source to the lower Gallinas River Receptor and San Augustine, shown by the size of the orange-shaded polygons. The very large polygon at McCallister Lake demonstrates the lake’s large cation-anion concentrations.

Na

Ca

Cl

SO4

0 100 2000 NaCl

SO4

Ca

0 100 2000

Ca

Na1000 2000 mg/l

Cl

SO4

0 100 2000 Na

Ca

Cl

SO4

LLoowweerr GGaalllliinnaassRReecceeppttoorr

SSaann AAuugguussttiinnee

GGrroouunndd WWaatteerr SSeeeeppss

UUppppeerr GGaalllliinnaass SSoouurrccee


MMoonntteezzuummaa PPoonndd

HHoott SSpprriinnggss


MMccCCaalllliisstteerr LLaakkee GGaalllliinnaass DDiivveerrssiioonn 22

0 100 2000 Na

Ca

Cl

SO4

CRESTON RIDGE

0 100 2000 Na

Ca

Cl

SO4

0 100 2000 Na

Ca

Cl

SO4Na

Ca

Cl

SO4

0 200 4000

Na

Ca

Cl

SO4

0 100 2000

SSttoorrrriiee LLaakkee GGaalllliinnaass DDiivveerrssiioonn 11

25

Figure 5. Histogram showing major cation concentrations in the sampled waters.

MAJOR CATIONS

0

200

400

600

800

1000

1200

1400

Ca Mg Na

mill

igra

ms

/ lite

r

Hermits Peak TrailheadSkating PondHot SpringsMiddle Gallinas River 1Middle Gallinas River 2Lower Gallinas RiverSt AugustinGallinas Canyon Seep 1Gallinas Canyon Seep 2Gallinas Canyon Seep 3Gallinas Canyon Seep 4Well (C.R.R. Ranch)McCallister LakeStorrie Lake

26

Figure 6. Histogram showing major anion concentrations in the sampled waters.

MAJOR ANIONS

0

500

1000

1500

2000

2500

3000

3500

4000

Cl SO4

mill

igra

ms

/ lite

r


27

Figure 7. Histogram showing dissolved halite (NaCl) and gypsum (CaSO4) concentrations in the sampled waters.

DISSOLVED MINERALS

0

1000

2000

3000

4000

5000

6000

NaCl CaSO4

mill

igra

ms

/ lite

r


28

Figure 8. Histogram showing hardness, conductivity, and total dissolved solid (TDS) measurements in the sampled waters.

ADDITIONAL PARAMETERS

0

2000

4000

6000

8000

10000

12000

Hardness Conductivity TDS


(CaCO3) (mg / L) (micromohs / cm)

29

TDS versus CONDUCTIVITY

y = 0.6389x - 166.49R2 = 0.9975

0

1000

2000

3000

4000

5000

6000

7000

8000

0 2000 4000 6000 8000 10000 12000CONDUCTIVITY

(micromohs / centimeter)

TOTA

L D

ISSO

LVED

SO

LID

S(m

illig

ram

s / l

iter)

Figure 9. Graph showing strong correlation between measured total dissolved solids and conductivity in the sampled waters.

Documents

WATER QUALITY ASSESSMENT IN THE GALLINAS WATERSHED, …